EP2577359B1 - Procédé et système permettant la détermination de la rigidité d'une couche géologique - Google Patents

Procédé et système permettant la détermination de la rigidité d'une couche géologique Download PDF

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EP2577359B1
EP2577359B1 EP11721784.4A EP11721784A EP2577359B1 EP 2577359 B1 EP2577359 B1 EP 2577359B1 EP 11721784 A EP11721784 A EP 11721784A EP 2577359 B1 EP2577359 B1 EP 2577359B1
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waves
layer
seismic
rigidity
geological
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EP2577359A2 (fr
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Francesco Mulargia
Silvia Castellaro
Mariapia Pastor
Gianluca Vinco
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Thur SRL
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Thur SRL
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    • G—PHYSICS
    • G01—MEASURING; TESTING
    • G01V—GEOPHYSICS; GRAVITATIONAL MEASUREMENTS; DETECTING MASSES OR OBJECTS; TAGS
    • G01V1/00—Seismology; Seismic or acoustic prospecting or detecting
    • G01V1/40—Seismology; Seismic or acoustic prospecting or detecting specially adapted for well-logging
    • G01V1/44—Seismology; Seismic or acoustic prospecting or detecting specially adapted for well-logging using generators and receivers in the same well
    • G01V1/48—Processing data

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  • the present invention refers to a method and to a system for determining the rigidity of a geological layer underlying another geological layer, which is preferably a surface layer delimited at the upper part by a free surface.
  • the invention refers to a method and system for determining the rigidity of a geological underlying a more rigid surface layer.
  • the measurement of the elastic properties, and in particular the rigidity, ⁇ , of the geological layers on which building foundations and generally building structures lie or into which they are submerged, may have various applications, among which the evaluation of the stability of the subsoil and thus the risk of collapse or permanent deformation of a building structure in the long term and/or in the case of a seismic event.
  • the classification of foundation subsoils according to the NEHRP (USA), Eurocode 8 (Europe) and NTC2008 (Italy) standards for designing seismic-resistant structures is mainly based on the velocity of the shear waves of a homogeneous layer equivalent to the first thirty metres of depth, V s30 .
  • An application of the measurement of the velocity of the elastic waves in the subsoil is the evaluation of the efficiency of the interventions for consolidating the subsoil beneath existent foundations, aimed at improving the elastic parameters, such as the Young's modulus and the rigidity modulus.
  • Indirect techniques based on surface measurements, i.e. neither inserting detector elements into the subsoil nor extracting samples from the subsoil and measuring their properties in a laboratory, are often used for measuring the velocity of the elastic waves.
  • indirect techniques are of seismic type, i.e. they are based on the analysis of the seismic waves produced by an artificial source.
  • the use of the conventional method of seismic prospection and i.e. generating - by means of suitable apparatus - longitudinal P and transverse S body waves and recording their refraction by the geological layers, with the ensuing identification and measurement of the elastic properties of the latter, is inefficient.
  • V i > V 2 the body wave is not refracted parallel to the interface and shall not be re-refracted in the surface layer.
  • the penetrometers are pressed in the ground, one of them being provided with piezoelectric transmitters, from which shear and primary waves are triggered by wave generator means. Waves propagate through the soil to a pair of receivers positioned at the same depth of the transmitters. The two penetrometers shafts are placed close to one another, namely at a fixed distance of about 20 cm.
  • WO 2004/019063 relates to a method of estimating the near surface weathering and sub weathering layer boundaries and the seismic velocities therein by the use of seismic waves emanating from a working drill bit in a well in a technique known as "seismic while drilling" or SWD.
  • US 6 094 401 describes a reverse vertical seismic profiling (VSP) system utilising an MWD (measurement while drilling) tool as downhole seismic source capable of generating a sweep of frequencies.
  • VSP vertical seismic profiling
  • MWD measurement while drilling
  • a frequencycontrollable modulator is used to provide a large force to the drill bit that is in contact with the formation by generating axial compressional (P-) waves. Since the bit can be in contact with the sidewalls of the borehole, it is said that the force generated by the modulator may also provide measureable transverse shear (S-) waves.
  • WO 2008/154640 discloses a method for obtained enhanced seismic data and optimised inverted reflectivities by using well control data to improve the quality of seismic processing and amplitude inversion.
  • the source is an apparatus which generates both P waves and S waves.
  • the interaction between these two types of waves in proximity to a surface gives rise, at a given distance from the source, to surface waves.
  • Energisation is typically actuated by means of a hammer which hits - once or several times - metal plates coupled to the surface of the ground to be explored. In this manner, wavefronts are generated which propagate through the underlying ground.
  • the surface layer comprising the foundations of a building structure typically has a rigidity greater than the rigidity of the underlying layer, which may be of different type (e.g. clay soil, sandy soil, etc).
  • a typical value of k is 0.2, thus the waves that have explored the underlying layer return to the surface with energy in the order of 0.04 and their identification among the waves that are trapped for reflection in the first layer (whose energy is much higher, in the order of 0.8) is practically impossible. Hence, the identification of the surface waves associated to the lower layer in the detected seismic traces and the measurement thereof are extremely difficult.
  • the Applicant has realised that if the active generator source of primary waves is positioned in the underlying layer whose rigidity is intended to be measured, the energy generated in the underlying layer is mostly available for characterizing the layer itself and is transmitted to the overlying layer solely after having "explored" the underlying one.
  • interface waves In particular, in case of energization in the underlying layer and in presence of an interface between two layers with different elastic properties with respect to each other (for example between two geological layers with different rigidity such as the foundation layer and the underlying layer), most of the energy is "trapped" in the underlying layer and it is represented by interface waves.
  • These waves called Stoneley waves, are entirely similar to Rayleigh surface waves and they propagate beneath the interface with the overlying layer with a simultaneously vertical and horizontal oscillation motion. Due to the continuity of displacements across the interface, the Stoneley waves extend also into the upper layer, exciting - by continuity - both the horizontal and vertical motions, but exponentially attenuating when moving away from the interface itself.
  • the waves whose frequency coincides with one of the vibration modes of the Rayleigh waves and of the Love waves in the overlying layer shall be the least attenuated among the transmitted waves.
  • the latter shall appear on the surface with more energy.
  • the detected waves are those that return to the surface after having explored the lower layer and having crossed the interface between lower and upper layer.
  • the Applicant has understood that by positioning the source of seismic waves in the layer whose rigidity is intended to be measured it is possible to detect at the surface the Stoneley waves, that occur at the surface as Rayleigh and Love surface waves modes. In particular, the Stoneley waves appear at the surface as higher modes of surface waves of Rayleigh and Love.
  • the present invention refers to a method according to claim 1 for determining the rigidity of a geological layer in terms of propagation velocity of the elastic waves within a geological system delimited by a free surface and comprising at least one first geological layer having a first rigidity and a second geological layer having a second rigidity and being arranged below the first geological layer, said first and second layer being separated from each other by an interface, the method comprising the steps of:
  • the step of determining a shear velocity of the elastic waves in the second layer comprises the following steps:
  • the method comprises the step of calculating the rigidity from the shear velocity of the elastic waves in the second layer.
  • the rigidity value of the first layer is greater than the rigidity value of the second layer.
  • the first geological layer is delimited by the free surface and comprises the foundations of a building structure.
  • the first layer has a thickness and the source is positioned at a depth with respect to the free surface larger than the thickness of the first layer.
  • the source of seismic signal is an impulsive source suitable to generate body waves.
  • the step of detecting at least one seismic signal comprises detecting a plurality of seismic signals and it is obtained by means of an array of sensors comprising a plurality of sensors arranged coupled with the free surface, each sensor being apt to detect a seismic signal of the plurality of seismic signals.
  • the surface waves whose propagation velocity is detected are detected through a multichannel technique.
  • the step of detecting at least one seismic signal comprises detecting a signal as a function of the time during a period of acquisition and the step of determining a map of the propagation velocity of the surface waves comprises performing a transformation of the seismic signal from the time domain to the frequency domain.
  • the present invention refers to a system according to claim 9 for determining the rigidity of a geological layer in terms of propagation velocity of the elastic waves within a geological system delimited by a free surface and comprising at least one first geological layer having a first rigidity and a second geological layer having a second rigidity and being arranged below the first geological layer, said layers being separated from each other by an interface, the system comprising a source suitable to generate seismic waves; at least one seismic signal sensor arranged coupled with the free surface, and an electronic unit for acquiring seismic signals detected by the at least one sensor, wherein said source is positioned in the second geological layer.
  • the at least one seismic signal sensor is an array of seismic signal sensors comprising a plurality of sensors, the plurality including a first and a last sensor, arranged coupled with the free surface at a predetermined spacing form each other.
  • the sensors are aligned along an alignment direction and the source is positioned at a predetermined distance from the first sensor of the linear array of sensors, defined along the alignment direction.
  • the source is positioned in the second layer at a depth comprised between 0.1 m and 2.0 m from the interface con the first layer.
  • the source of seismic waves is energized by a depth seismic gun.
  • the present invention refers to a method and to a system for measuring the rigidity of a geological layer positioned beneath the foundations of buildings and building structures in general, which constitute or are included in a surface layer delimited at the upper part by the free surface of the ground and indicated as foundation layer.
  • the characterisation of the geological layers according to the method and system according to the present preferred embodiment may be performed both before a ground consolidation intervention and after the intervention with the aim of evaluating the effectiveness of intervention itself.
  • the subsoil in the first approximation, it is possible to describe the subsoil as a stratified medium wherein the main variation of the composition and of the mechanical properties occurs along the depth, while the variation in the two horizontal directions is negligible.
  • the layers are defined starting from the surface: the first layer shall be the surface one, the second shall be the underlying one and so on and so forth.
  • the method according to a particular aspect of the present invention is apt to measure the velocity of the elastic waves in a geological system comprising at least one first layer of the subsoil 6 and a second geological layer 5 underlying with respect thereto.
  • the first layer is that whose upper surface is the free surface 2.
  • the interface between the upper layer (first) 6 and the lower layer (second) 5 is indicated with reference number 3.
  • the first geological layer 6 is a foundation layer comprising the foundations of a building structure, for example a residential building 1.
  • the system for measuring the elastic waves which are propagated in the geological system comprises a source 4 (shown in figure 3 ) apt to generate elastic body waves and an array of sensors 8 comprising a plurality of sensors 8a, 8b, ..,8j, each of which being apt to detect elastic surface waves which propagate along the free surface 2 of the ground.
  • the array of sensors is a linear array in which the sensors are arranged in line at a given spacing between a sensor and the next adjacent sensor ( figure 3 ).
  • the array of sensors is constituted by ten sensors with constant spacing ⁇ x.
  • a plurality of sensors is to be intended comprising at least two sensors, preferably between 4 and 12 sensors.
  • the spacing between the sensors may be of a different value from one sensor to another sensor or generally be non-constant.
  • the method is apt to measure the surface waves produced by primary and secondary waves generated by a source located within a second geological layer underlying a first geological layer, the source being positioned at a predetermined depth greater than the thickness of the first layer, e.g. the foundation layer.
  • the method is apt to measure, at the surface, the surface waves produced by the Stoneley interface waves.
  • the source is located at a depth t > s.
  • the source is an impulsive seismic source and comprises at least one explosive charge with initial velocity comprised between 300 and 700 m/s.
  • the source comprises an explosive charge with an initial velocity of 500 m/s and insertion time ⁇ 1ms.
  • the source 4 is positioned at a depth t, greater than the thickness s of the foundation layer, within a hole 9 (indicated in figure 3 ) which extends from the free surface through the geological system.
  • a hole 9 indicated in figure 3
  • the position of the source 4 along the z-axis (depth) is indicated with 7.
  • the source is apt to generate interface and surface seismic waves.
  • the energization of the source is provided by means of a depth seismic gun, schematically illustrated in figure 4 and indicated in its entirety with reference number 10.
  • the seismic gun has been particularly designed to operate at a greater depth than normal seismic guns.
  • the depth seismic gun comprises a barrel 11, of length suitable to reach the depth t, the barrel being inserted into the ground, inside the lower geological layer (or reaching the lower layer), into a previously made hole (e.g. hole 9 in figure 3 ).
  • the length of the barrel 11 of the seismic gun is at least 2 metres long, for example comprised between 2 and 3 metres, so as to be able to position and detonate the explosive charge, i.e. a cartridge, inside the underlying layer.
  • the gun comprises a plate 12 for laying on the ground surface, a support knob 13 and a trigger knob 14.
  • the end 15 of the barrel 11 is engaged to a removable explosion chamber 16, with open bottom, into which the cartridge of the industrial type, per se known and available in the market, is inserted.
  • the explosion of the cartridge may be performed by the free surface, by operating on the trigger knob 14 which mechanically hits an ignitor (not shown in the figure), generating the explosion of the cartridge, by means of a device (not shown in the figure) extending along the barrel 11.
  • the sensors of the array of sensors 8 are geophones, i.e. elastic waves electromechanical transducers.
  • each geophone 8a, ...., 8j is recorded separately but synchronously on the different geophones.
  • a relation between the wavelength and the thickness of the explored layer holds for the surface waves and for the layer waves.
  • the components with large wavelength, ⁇ provide information regarding layers with greater depths
  • components with small wavelength ⁇ provide information regarding layers closer to the surface.
  • V ⁇ ⁇ f holds, where V is the velocity of the waves and f the frequency thereof. Considering the same velocity, the components with large wavelength ⁇ are the low frequency ones and those with small wavelength ⁇ are the high frequency ones.
  • each sensor 8a, 8b, ..., 8j is a geophone with frequency comprised between 4 and 10 Hz.
  • the geophones 8a, .., 8j of the array 8 are horizontal motion geophones, suitable for detecting the velocity of the surface waves with transverse horizontal polarisation, i.e. Love waves.
  • the geophones are vertical motion geophones, suitable for detecting the velocity of the Rayleigh waves.
  • the measuring method comprises the generation of a shot "outside" the sensors line, i.e. the source is arranged at a predetermined distance D, defined along the direction of arrangement of the sensors (x-axis), from the nearest sensor, i.e. first sensor 8a, of the array.
  • D is not smaller than 5 m, more preferably it is comprised between 6 and 20 m.
  • the array of sensors is linear along an aligning direction (axis x) and the source is arranged on the extension of the sensors alignment.
  • the source is not arranged aligned with the array of sensors, but it is slightly displaced with respect to the aligning position in the plane (y,z), indicated with reference number 7 in figure 2 .
  • the array of sensors is developed according to a two-dimensional geometry, such as for example according to an X, T or L-shaped arrangement.
  • the minimum spacing between the sensors is in relation with the minimum detectable wavelength, thus with the detectable minimum depth.
  • the minimum spacing is comprised between 0.5 and 2 m.
  • the sensors of the array of sensors are equally spaced from each other, with spacing ⁇ x between 0.5 and 2 m.
  • the distance between the first and the last sensor of the array referred to as the detection length and indicated with L, represents the length of the detection coverage of the system and it is in relation with the maximum wavelength, thus with the maximum detectable depth.
  • the step of recording the surface waves is carried out according to the multi-channel analysis of surface waves (MASW) technique.
  • the sensors are typically coupled to the soil by means of rods while on floors/foundations tripods are used.
  • the sensors 8a, 8b,...,8j, synchronised in acquisition are connected, through a connection line 17, to a data acquisition line 18, preferably a digital multichannel seismograph with a number of channels at least equal to the number of sensors, which may be a commercial seismograph (e.g. Rosina produced by Micromed spa).
  • the data acquisition unit may comprise or may in turn be connected with a central processing unit 19, for example a personal computer (PC).
  • the acquisition of seismic traces occurs starting from the exceedance of a preset threshold ("trigger", coinciding with the instant of energization of the subsoil) and it lasts for a few seconds after said event.
  • the data acquisition unit saves the data regarding a brief period preceding the exceeding of the threshold ("pre-trigger"), said period lasting a few seconds or a few fractions of a second preceding the instant when the threshold is exceeded.
  • the seismic traces are recorded by each sensor as a function of the time, thus obtaining a plurality of amplitude/time signals, each signal being detected by the respective sensor of the array of sensors.
  • Phase velocity spectra of the surface waves and the respective experimental dispersion curves are obtained through a transformation from the amplitude/time domain to the wave frequency/number domain (f-k) or slowness/frequency domain (p-f), or to the velocity/frequency domain (V-f), according to the processing methods known in the MASW field technique.
  • Such technique is generally efficient at isolating the surface waves from the body waves (P and S), the first generally constituting the main portion of the seismic trace in presence of a sufficiently far energization, e.g. of a source located sufficiently far from the sensor array.
  • a dispersion curve is calculated by searching the maximum values of spectral power in the space f-k or p-f, so as to form a 2D image of the phase velocity of the Rayleigh and/or Love waves as a function of the frequency, which is in turn linked to the depth.
  • the step of determining the velocity of the surface waves comprises the following steps:
  • Carrying out steps 1)-4) for different test velocities produces a data matrix which is represented in a two-dimensional plot frequency-V i , generally represented coloured, where the colours are proportional to the power spectra under step 4).
  • V i the power spectral density for a given pair of velocity and frequency
  • the maximum values in the spectral plots indicate the velocity at the various frequencies of the different propagation modes of surface waves, i.e. fundamental or higher-order modes, excited by the Stoneley waves, which thus appear as surface waves, both Rayleigh and Love surface waves.
  • the Stoneley waves appear at the surface as surface waves of both Rayleigh and Love type.
  • dispersion The variation of the velocity as a function of the frequency is called dispersion.
  • the step of determining a shear velocity of the elastic waves in the second layer comprises the following steps:
  • the at least one seismic signal comprises detecting a plurality of seismic signals and it is obtained by means of an array of sensors comprising a plurality of sensors arranged coupled with the free surface, each sensor being apt to detect a seismic signal of the plurality of seismic signals and the step of detecting the plurality of seismic signals comprises positioning the array of sensors on the free surface and the step of determining the propagation velocity comprises determining, from the plurality of seismic signals, the propagation velocity of Rayleigh and Love surface waves coupled to the interface Stoneley waves.
  • Figure 5 is an exemplifying image of experimental dispersion, in the phase frequency-velocity domain, obtained from the analysis of the seismic traces measured in a geological system of two layers, in which the upper layer is constituted by the foundations and has a thickness s of 1.3 m.
  • two distinct high energy regions are visible (in the grey scale, the greater energy corresponds to a lighter tonality), which are substantially attributable to two dominant modes of propagation of the surface waves, Love waves in this case: a first low frequency region extended from about 20 to 30 Hz (where there is a high density of maximum energy points, represented by white circles) and a second high frequency region which is extended approximately from 35 to 80 Hz. From the maximum energy points in each region there follows the identification of dispersion curves which indicate at what phase velocity the maximum transport of energy of the Love waves occurs as a function of frequency and thus of the explored depth.
  • the first region is attributable to a first mode of the Love waves with a phase velocity of about 150 m/s and the second region is attributable to a second Love mode with a phase velocity of about 300 m/s.
  • the consolidation intervention may occur for example by providing a plurality of holes through the layer of the ground to be consolidated (i.e. the lower layer 5) and subsequently injecting an expanded resin for filling the holes, according to known techniques.
  • Figure 6 is the dispersion image obtained from recording the seismic traces after the consolidation intervention.
  • Figure 6 shows the creation of a "channel" in which the waves not present in figure 5 travel, at a frequency between 30 and 45 Hz, i.e. an increase of rigidity in the layer in which the waves travel in this frequency range.
  • the points of maximum spectral power (white circles) for the first region extend now approximately from 30 to 45 Hz with phase velocity of about 200 m/s, while the points of maximum spectral power for the second region extend from about 55 to 100 Hz, with velocity of about 300 m/s. From a comparison of the image of figure 6 with an image of figure 5 it is concluded that the phase velocity for the first mode of the Love waves, associated with the deepest layer, is increased by about 30%. Both the velocity of the Rayleigh and Love surface waves is very close to that of the shear waves S, therefore the velocity value measured through the aforedescribed method represents, with good approximation, the value of the shear velocity Vs.
  • the so-called inversion process allows to obtain a theoretical dispersion curve almost similar to the experimental dispersion curve, according to algorithms, per se known, for modelling of surface waves in multilayer systems.
  • the calculation procedure thus allows to obtain, the profile of shear velocity, Vs, as a function of the depth, z. From the determination of the profile of shear velocity V s (z) the rigidity of the ground is obtained, and in particular the rigidity of layer underlying the foundations, ⁇ , given by the relation (1).

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Claims (11)

  1. Procédé permettant la détermination de la rigidité d'une couche géologique en termes de vitesse de propagation des ondes élastiques à l'intérieur d'un système géologique délimité par une surface libre (2) et comprenant au moins une première couche géologique (6) ayant une première rigidité et une épaisseur (s) et une seconde couche géologique (5) ayant une seconde rigidité et étant agencée au-dessous de la première couche géologique,
    dans lequel la première couche est délimitée par la surface libre et comprend les fondations d'une structure de bâtiment (1) et possède une première valeur de rigidité et la seconde couche possède une seconde valeur de rigidité, la première valeur de rigidité étant supérieure à la seconde valeur de rigidité et lesdites première et seconde couches étant séparées l'une de l'autre par une interface (3), le procédé comprenant les étapes consistant à :
    - positionner une source (4) à l'intérieur de la seconde couche géologique (5), dont la rigidité est destinée à être mesurée, la source étant apte à générer des ondes sismiques et étant située à une profondeur (t) comprise entre 0,1 m et 2 m par rapport à l'interface (3) ;
    - activer ladite source d'ondes sismiques ;
    - détecter au moins un signal sismique au moyen d'un réseau de capteurs (8) agencé en étant couplé à la surface libre et positionné sur la surface libre, dans lequel le réseau de capteurs comprend une pluralité de capteurs (8a, ..., 8j), dans lequel l'au moins un signal est une pluralité de signaux sismiques et chaque capteur de la pluralité est apte à détecter un signal sismique de la pluralité de signaux sismiques ;
    - déterminer à partir de l'au moins un signal sismique une vitesse de cisaillement des ondes élastiques dans la seconde couche et qui est par conséquent indicative de la rigidité de la seconde couche, et
    - calculer la rigidité à partir de la vitesse de cisaillement des ondes élastiques dans la seconde couche.
  2. Procédé selon la revendication 1, dans lequel l'étape de détermination d'une vitesse de cisaillement des ondes élastiques dans la seconde couche comprend les étapes suivantes :
    - déterminer à partir d'au moins un signal sismique la vitesse de propagation des ondes de surface de Rayleigh et de Love couplées à des ondes d'interface de Stoneley, les ondes de surface et d'interface étant provoquées par les ondes sismiques générées par ladite source ;
    - déterminer une carte desdites vitesses de propagation des ondes de surface en fonction de leur fréquence ;
    - identifier, dans la carte des vitesses, une vitesse de propagation dont la fréquence est corrélée avec une profondeur dans le système géologique, et
    - mettre en corrélation au moins une vitesse de propagation identifiée dans la carte des vitesses avec une vitesse de cisaillement des ondes élastiques dans la seconde couche (5) et qui est par conséquent indicative de la rigidité de la seconde couche.
  3. Procédé selon l'une quelconque des revendications précédentes, dans lequel la première couche géologique est délimitée par la surface libre et comprend les fondations d'une structure de bâtiment (1).
  4. Procédé selon l'une quelconque des revendications précédentes, dans lequel ladite source de signal sismique est une source impulsive appropriée pour générer des ondes de volume.
  5. Procédé selon la revendication 2, dans lequel l'étape de détection de la pluralité de signaux sismiques consiste à positionner le réseau de capteurs sur la surface libre et l'étape de détermination de la vitesse de propagation consiste à déterminer, à partir de la pluralité de signaux sismiques, la vitesse de propagation d'ondes de surface de Rayleigh et de Love couplées aux ondes de Stoneley d'interface.
  6. Procédé selon la revendication 1, dans lequel les ondes de surface dont la vitesse de propagation est détectée sont détectées par une technique à canaux multiples.
  7. Procédé selon la revendication 2, dans lequel l'étape de détection d'au moins un signal sismique consiste à détecter un signal en fonction du temps pendant une période d'acquisition et l'étape de détermination d'une carte de la vitesse de propagation des ondes de surface consiste à réaliser une transformation du signal sismique du domaine temporel au domaine fréquentiel.
  8. Procédé selon la revendication 4, dans lequel la source impulsive comprend au moins une charge explosive ayant une vitesse initiale comprise entre 300 et 700 m/s.
  9. Système permettant la détermination de la rigidité d'une couche géologique en termes de vitesse de propagation des ondes élastiques à l'intérieur d'un système géologique délimité par une surface libre (2) et comprenant au moins une première couche géologique (6) ayant une première rigidité et une seconde couche géologique (5) ayant une seconde rigidité et étant agencée au-dessous de la première couche géologique, lesdites couches étant séparées l'une de l'autre par une interface (3), le système comprenant
    une source appropriée pour générer des ondes sismiques ;
    un réseau de capteurs de signal sismique (8) comprenant une pluralité de capteurs (8a, ..., 8j), la pluralité incluant un premier (8a) et un dernier (8j) capteur, agencé en étant couplé à la surface libre, le réseau de capteurs étant positionné sur la surface libre, et
    une unité électronique (18) pour acquérir des signaux sismiques détectés par l'au moins un capteur,
    dans lequel ladite source est positionnée dans la seconde couche géologique à une profondeur (d) comprise entre 0,1 m et 2,0 m par rapport à l'interface (3), la première couche possède une valeur de rigidité supérieure à la valeur de rigidité de la seconde couche, et la première couche est délimitée par la surface libre et comprend les fondations d'une structure de bâtiment (1).
  10. Système selon la revendication 9, dans lequel les capteurs sont alignés le long d'une direction d'alignement et la source est positionnée à une distance prédéterminée (D) du premier capteur du réseau linéaire de capteurs, définie le long de la direction d'alignement.
  11. Système selon l'une quelconque des revendications 9 et 10, dans lequel la source d'ondes sismiques est excitée par un canon sismique en profondeur (10).
EP11721784.4A 2010-05-28 2011-05-27 Procédé et système permettant la détermination de la rigidité d'une couche géologique Active EP2577359B1 (fr)

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EP10425184.8A EP2390683B1 (fr) 2010-05-28 2010-05-28 Méthode et système pour déterminer la rigidité d'une couche géologique
EP11721784.4A EP2577359B1 (fr) 2010-05-28 2011-05-27 Procédé et système permettant la détermination de la rigidité d'une couche géologique
PCT/EP2011/058743 WO2011147970A2 (fr) 2010-05-28 2011-05-27 Procédé et système permettant la détermination de la rigidité d'une couche géologique

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US10371840B2 (en) * 2016-07-08 2019-08-06 Sercel Tension monitoring method and system for towed antenna
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US4399525A (en) * 1979-10-05 1983-08-16 Chevron Research Company Method for interpreting well log records to yield indications of gas/oil in an earth formation such as a sandstone, limestone, or dolostone
US5012453A (en) * 1990-04-27 1991-04-30 Katz Lewis J Inverse vertical seismic profiling while drilling
US5080190A (en) * 1991-06-14 1992-01-14 Southwest Research Institute Reversible rigid coupling apparatus and method for borehole seismic transducers
US5901113A (en) * 1996-03-12 1999-05-04 Schlumberger Technology Corporation Inverse vertical seismic profiling using a measurement while drilling tool as a seismic source
US6292754B1 (en) * 1999-11-11 2001-09-18 Bp Corporation North America Inc. Vector recomposition of seismic 3-D converted-wave data
US6665618B1 (en) * 2002-08-14 2003-12-16 Conocophillips Company Seismic survey design technique
US6868037B2 (en) * 2002-08-20 2005-03-15 Saudi Arabian Oil Company Use of drill bit energy for tomographic modeling of near surface layers
US7082831B2 (en) * 2003-05-13 2006-08-01 Zeng Xiangwu Measurement of base and subgrade layer stiffness using bender element technique
US7826973B2 (en) * 2007-06-15 2010-11-02 Chevron U.S.A. Inc. Optimizing seismic processing and amplitude inversion utilizing statistical comparisons of seismic to well control data

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WO2011147970A2 (fr) 2011-12-01
EP2577359A2 (fr) 2013-04-10
EP2390683B1 (fr) 2020-04-08
PT2390683T (pt) 2020-05-20
CA2800190A1 (fr) 2011-12-01
PT2577359T (pt) 2020-07-02
WO2011147970A3 (fr) 2012-06-28
ES2787231T3 (es) 2020-10-15
ES2799885T3 (es) 2020-12-22
EP2390683A1 (fr) 2011-11-30
US20130077437A1 (en) 2013-03-28

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